Methods and preliminary results

The drilling profile line started from the shoreline at the base of the snow-covered Ice Complex cliff (Figure 4.7-3). The profile consisted of 11 boreholes (1 to 32.5 meters deep). 10 seawater samples and 19 core samples for grain size, mineralogical and chemical analysis were collected. Because of distinctive cone-like drilling in liquefied bottom sediment it was impossible to collect a complete core. The near-bottom water temperature was measured during the drilling process.

Average erosion retreat rate of the ice-rich coast at the beginning of the drilling profile is 5.8 m/year, taking into account that the average erosion rate for the whole adjoining coastal segment is about 3-4.5 m/year. These data were obtained during our previous studies (Grigoriev et al., 2000) and by comparison of up-to date measurements with remote sensing materials.

The base of Ice Complex deposits was found near the shore in a depth of 3 meters below sea level. The underlying sand deposits were discovered down to the depth of 30 meters below sea level. The deepest borehole reached 32.5 meters and showed some unexpected results (Figure 4). Despite of a high coastal erosion rate and very low water temperatures (from -1.3 to -2.1 ºC) the inclination of the permafrost table in a distance of 1.3 km from the shore was very steep (0.015) and from 1.3 to 1.4 km – extremely steep (more than 0.3).

This anomaly is probably explained by ancient thermokarst processes under sub aerial conditions. Estimation show that the average rate of permafrost table degradation is about 8 cm/year or slightly more at the studied transect.

4.7.1.3 Further investigations

In order to study the sub-sea permafrost evolution within the whole shore face profile near the Cape Mamontov Klyk a deeper drilling (up to 300 m depth) is planned in spring 2005. The main tasks of this drilling campaign are:

- To drill a longitudinal borehole profile by professional drilling machine;

- To determine the sub-sea permafrost table up to 10-15 km from the shore;

- To characterise the sediments;

- To analyse temperature and salinity distribution in the boreholes;

- To estimate rates of permafrost degradation depending on coastal erosion activity and other factors

4 Periglacial features around Cape “Mamontov Klyk” The Expedition Lena-Anabar 2003

Figure 3: The beginning of drilling profile at the shore (April, 2003).

Figure 4: Reconnoitring drilling profile of degraded continental offshore permafrost at the Cape Mammoth Tusk Area, Laptev Sea (April, 2003).

Acknowledgements

The success of the spring part of expedition “Lena 2003” would not been possible without help of the Tiksi Hydrographical Base team, which organized field transportation and drilling assistance (Victor Dobrobaba, Vladimir Yakshin, Timophey Sidorov, Alexander Saphin and Sergey Kamanin). Special thanks to Dmitry Melnichenko, head of the Tiksi Hydrographical Base.

4.7.2. Measurements of the coast relief in the area of Mamontov Klyk and ice and sediment sampling

Mikhail N. Grigoriev and Waldemar Schneider

4.7.2.1. Introduction

One of the main tasks of the expedition “Lena 2003” was an estimation of coastal erosion retreat rates at the about three kilometer long coastal segment in the area of Mamontov Klyk. One of a reasons of these studies is the beginning of the new Laptev Sea System Project “Dynamics of Permafrost”. In the frame of this project, during spring 2005, a relatively deep profile consisting of a number of boreholes (up to 200-250 meters in depth) is aimed in that area.

4.7.2.2. Methods

Geodetic measurements have been carried out at the key site, using a laser theodolite Elta 50 R, to obtain the modern horizontal and altitudinal position of the shore line (Figure 4.7-5). Theodolite profiles and benchmarks recorded in the field were identified and compared with the aerial photographs and maps. At erosional shores the position of the cliff base and the cliff upper edge was measured. Characteristic terrestrial features, which could also be identified on aerial photographs, such as sharp turns of small streams, small water bodies, boundaries of different types of vegetation etc., served as natural marks. A number of aerial photographs (scales 1: 30,000 – 1:50,000) and topographic maps (scales 1:25,000-200,000) were analysed. Theodolite profiles and benchmarks recorded in the field could be identified in the remote material.

Furthermore, aerial photos and maps are used for long-term analysis of coastal dynamics of the key sites by computer techniques, which allow us to estimate an average rate of shoreline retreat and long-term trends of the Laptev Sea coast quite precisely.

The undisturbed sediment and ice wedge sampling was conducted from the key coastal section by chain saw (Figure 4.7-6).

Detail information concerning general goals and methods of multi-stage coastal studies of Joint German-Russian expedition is presented in previous Reports of Polar Research (Rachold, Grigoriev, 1999, 2000, 2001; Pfeiffer, Grigoriev, 2002; Grigoriev et al., 2003).

4 Periglacial features around Cape “Mamontov Klyk” The Expedition Lena-Anabar 2003

Figure 4.7-5. Theodolite survey of the coastal cliff top in the area of Mamontov Klyk (August 2003)

Figure 4.7-6. Coastal sediment and ice wedge sampling by chain saw (area of Mamontov Klyk, August 2003)

4.7.2.3. Preliminary results

The coasts of studied area mainly consist of Ice Complex deposits, which are eroded very fast (Figure 4.7-7). Primary coastal forms are: cliffs, solifluction slopes (Figure 4.7-8), alas remnants and gullies. In 2000, the first measurement of coastal erosion rates at the area of Cape Mamontov Klyk was carried out by coastal team of the Expedition “Lena 2000”. It was determined that the average retreating rates of ice-rich cliff tops and cliff base of the whole observed coastal sector for long-term period (1971-2000) are about 4.0 and 4.4 m/year, respectively (Grigoriev et al., 2001).

Figure 4.7-7. 20 meters altitude icy cliff west of Mamontov Klyk Cape (August 2003) In 2003, at this site additional coastal line measurements and observations were carried out. They have shown that the average coastal retreat rate of studied shore has kept the same range as in the previous period (about 4.0 m/year). Most active coastal retreat takes place in the sections, where the

“block” type of shore destruction takes place (Figure 4.7-9). The maximum velocity of coastal erosion was observed at the local limited shore section west of the Nyuchcha-Dzhiele River mouth (up to 6 m/year) and west of Cape Mamontov Klyk (5.8 m/year). Quite moderate retreat rates have been determined on the coastal segments adjacent to mouth of the Nyuchcha-Dzhiele River and Mamontov Klyk Cape (1-3.5 m/year).

4 Periglacial features around Cape “Mamontov Klyk” The Expedition Lena-Anabar 2003

Figure 4.7-8: Typical solifluction slope adjacent to Ice Complex shore (area of Mamontov Klyk, August 2003)

Figure 4.7-9.:The “block” type of destruction of the ice-rich shore (west of mouth of the Nuchcha-Dzhiele River)

According to the task of Arctic Coastal Dynamics (ACD) Project, a number of undisturbed sediment and ice wedge samples were collected from the key coastal section and transported to Germany (Table 4.7-1). This site is located in the beginning of prospective drilling profile.

Table 4.7-1: Frozen sediment and ice wedge samples (August 2003)

No. Name and depth Coordinates Description Number of

samples 1 MAK-VI (1-5)

Cape Mamontov Klyk

73-36-26.9 N 117-10-38.9 E

Ice block (10x10x10 cm)

5 2 MAK-VS (1-5)

Cape Mamontov Klyk

73-36-26.9 N 117-10-38.9 E

Ground block (10x10x10 cm)

5

4.7.1.4. Further investigations

We plan to continue a coastal study and sampling in the area of Cape Mamontov Klyk in the future. Probably in 2005 a deep drilling will be conducted in the coastal zone of that area. Investigated coastal segment belongs to the largest coastal section (120 km) of the Laptev Sea, which almost continuously consists of Ice Complex deposits. This segment is one of the most active in respect of coastal erosion and play a very important role in sediment and organic carbon balance of the Laptev Sea.

4 Periglacial features around Cape “Mamontov Klyk” The Expedition Lena-Anabar 2003

4.7.3 Shore face profiles in the area of Cape Mamontov Klyk: echo sounding, seawater and sea bottom deposits sampling Mikhail N. Grigoriev and Waldemar Schneider

4.7.3.1. Introduction

One of the tasks of the expedition “Lena-Anabar 2003” was a determination of shore face features in the area of Cape Mamontov Klyk at the adjacent near-shore shelf. In this region, a bathymetric survey, seawater and bottom sediment sampling were carried out in August 2003. The main reason of seabed research is a purpose to conduct a relatively deep drilling on the shallow shelf from the sea ice in the nearest future. Previous shore face investigations in this sector of the Laptev Sea (near Terpay-Tumsa Cape) have been carried out in 2000 (Are et al., 2001).

4.7.3.2. Methods

Bathymetric studies were conducted with help the echo-sounding device and rubber boat with “Honda” engine. The field of bathymetric survey has occupied an area about 60 km² (4 x 15 km), between isobath 1 and 10 meters (Figure 4.7-10). The length of all bathymetric profiles exceeds 150 km. For bottom sediment and seawater sampling a standard sampling dredger and bathometer were used.

4.7.3.3. Preliminary results

As a result of bathymetric survey the bathymetric scheme of studied seabed was created. The mean shore face inclination at that part of the shelf is extremely slightly, about 0.0007. At least two quite evident sub-sea terraces (or terrace-like surfaces) were discovered at the shore face. The first vast sub-sea terrace is over the range of depth about 5-6 meters and another terrace begins from 9.5 meters depth (see Fig. 4.7-10).

It is very interesting that a few years ago approximately the same sub-sea terraces were found near the Cape Terpay-Tumsa in 60 km east of the Cape Mamontov Klyk (Are et al., 2001). Probably, these forms are results of several stages of coastal erosion activity. Taking into account that an average coastal retreat rate for the whole studied coast is about 4.0 m/year, the shallow sub-sea terrace, placed from 4.5 km to 11.5 km from the shoreline, was formed during a period of about 2900-1000 years BP. It is very difficult to evaluate the age of formation of the deeper terrace, beginning in a distance of about 14.5 km from the coast. It is possible that this terrace was formed during first stage of sea level stabilization in Holocene (about 5000-3600 years BP).

Figure 4.7-10. Bathymetric scheme and the shore face relief adjacent to the Mamontov Klyk Cape area (August 2003). Bathymetric profiles - white dotted line. Vertical white line is a location of proposed drilling profile.

4 Periglacial features around Cape “Mamontov Klyk” The Expedition Lena-Anabar 2003

During summer fieldwork 30 bottom sediments samples were collected from 0 to 10 meters depth as well as ice and frozen sediment samples from the coastal outcrops for different types of analysis, which were transported to Germany (Tabs. 4.7-2, 4.7-3). At present time all samples are processed in the laboratories.

Table 4.7-2: List of bottom sediment samples, Profile MAK-3 (August 2003)

No. Name Water depth

Table 4.7-3: Frozen water and frozen sediment samples „Lena – Anabar 2003“

N o.

Name Depth

(Water depth / Depth of sampling)

Description Number

of samples 1 MAK-3 0m; 2,5m; 5m; 7,5m; 10m Frozen sea water

samples

5 2 MAK-3 7/0m; 7/3,5m; 7/7m; 10/0m;10/5m;10/10m

0m;2,5/0m;5/0m;5/5m;

Frozen sea water sample (Unfiltered)

10 3 MAK-3 0/0m; 2,5/0m; 5/0m; 5/5m;

7/0m; 7/3,5m; 7/7m; 10/0m; 10/5m;

10/10m)

Frozen sea water sample (Filtered)

10

4.7.3.4. Further investigations

The study of shore face profile structure and dynamics in the area of Cape Mamontov Klyk will be continued in spring 2005. The new facts concerning development of the shore face could be very useful for study of sub-sea permafrost evolution and regional paleogeographical reconstructions on the whole.

4.8. References

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Boyarsky O.G. and Mitt K.L. (1961). New data on relic ground ice in Olenek-Anabar tundra.

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Calhoun, A. and King, G.M. (1997). Regulation of root-associated methanotrophy by oxygen availability in the rhizosphere of two aquatic macrophytes. Appl. Environ. Microbiol. 63 (8): 3051-3058.

Cao, M., Marshall, S. and Gregson, K. (1996). Global carbon exchange and methane emissions from natural wetlands: application of a process-based model. J. Geophys. Res. 101 (D9): 14399-14414.

Chekanovsky N.L. (1896). The daybook of the expedition at rivers Nizhniaya Tunguska, Olenek and Lena in 1873-1875. Transactions of Russian Geographical Society, v. XX, ? 1, (In Russian).

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GrigorievM. N., Rachold V., Are F. E., Hubberten H.–W., Razumov S. O., and W. Schneider (2001). Coastal erosion in the Western coast of the Laptev Sea (2001). In: The Lena Delta expedition 2000. Reports on Polar Research, Bremerhaven, Germany, 335, p. 54-60.

GrigorievM. N., Rachold V., Bolshiyanov D.Yu., Pfeiffer E.-M., Schirrmeister L., Wagner D., and H.-W. Hubberten (Eds.) (2003). Russian-German Cooperation SYSTEM LAPTEV SEA 2000: The Expedition LENA 2002. Reports on Polar and Marine Research, 466, Bremerhaven, Germany, 341 pp.

Grigoriev M.N. (1993). Cryomorphogenesis of the Lena River mouth area. Permafrost Institute SB AN USSR, Yakutsk, Russia. 176 pp. (In Russian).

Grigoriev N.F. (1966). Permafrost in the Yakutian coastal Zone. Nauka Press, Moscow, Russia, 180 pp. (In Russian)

Grigoriev, M.N., and V.V. Kunitsky (2000). Ice Complex of Yakutian Arctic Coast as a Sediment Source on the Shelf.: Hydro meteorological and Biogeochemical Studies in the Arctic.

Vladivostok: Arctic Regional Centre, Far-Eastern Branch of RAS, Vol. 2, pp. 109-116 (in Russian).

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Meyer, H., A. Yu. Dereviagin, C. Siegert, L. Schirrmeister, and H.-W. Hubberten (2002b).

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Pfeiffer, E.-M., Akhmadeeva, I., Becker, H., Friedrich, K., Wagner, D., Quass, W., Zhurbenko, M., Zöllner, E., Boike, J. (1999). Modern Processes in Permafrost Affected Soils. In:

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“Quaternary geology and geomorphology of Siberia”. Novosibirsk, Publications of IGiG SO AN SSSR, v. 27., p. 102-117. (In Russian).

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Rachold V., and M. N. Grigoriev (Eds.) (2000). Russian-German Cooperation SYSTEM LAPTEV SEA-2000: The Expedition LENA 1999. Reports on Polar Research, 354, Bremerhaven, Germany, 269 pp.

Rachold V., and M. N. Grigoriev (Eds.) (2001). Russian-German Cooperation SYSTEM LAPTEV SEA-2000: The Expedition LENA 2000. Reports on Polar Research, 388, Bremerhaven, Germany, 135 pp.

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Roulet, N.T., Jano, A., Kelly, C.A., Klinger, L.F., Moore, T.R., Protz, R., Ritter, J.A. and Rouse, W.R. (1994). Role of the Hudson Bay lowland as a source of atmospheric methane. J.

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Schirrmeister, L., Grosse, G., Schwamborn, G., Andreev, A.A., Meyer, Kunitsky, V.V., Kuznetsova, T.V., Dorozkina, M.V., Pavlova, Y.Y, Bobrov, A., Oezen, D. (2004). Late Quaternary history of the accumulation plain north of the Chekanovsky Ridge (Lena Delta, Russia). A multidisciplinary approach.- Polar geography, 27: 277-319.

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4 Periglacial features around Cape “Mamontov Klyk” The Expedition Lena-Anabar 2003

4.9. Appendices

Appendix 4-1. Surface parameters for the studied geolocated sites

around Cape Mamontov Klyk ……… 155

Appendix 4-2. Active layer data of the geo-located sites……….. 170

Appendix 4-3. List of soil samples (active layer); collected in the

coastal lowland……… 171

Appendix 4-4. List of permafrost sediment and paleosol samples for

microbiological, molecular biological and biochemical analyses……….. 172

Appendix 4-5. List of sediment samples……….. 173

Appendix 4-6. List of ice and water samples……….. 182

Appendix 4-7. Collection of bone samples……….. 189

The Expedition Lena-Anabar 2003

-1. Surface parameters for the studied geolocated sites around Cape Mamontov Klyk

Site Latitude Longitude Date Major relief type Relief position

features inclination slope (°)

Soil moisture Water bodies depth (cm) Mklyk 73,6073 117,1249 08. 08Edoma lower slope thermokarst hills very gently 3 moderate moist - - yes

212 73,6109 117,1268 10. 08River valley (mouth) terrace sand bank flat 1 moist - - -

213 73,6069 117,1925 10. 08Ovrag (mouth) medium slope - very steep 65 moist - - -

214 73,6051 117,1994 10. 08Edoma elevated plain - very gently 2,5 dry - - yes

215 73,6045 117,2102 10. 08Ovrag (mouth) medium slope mud flows very steep 65 very moist - - yes 216 73,5955 117,2475 10. 08Marine terrace lower plain - flat 1,5 very moist small ponds n.a. yes

217 73,5976 117,2365 10. 08Log floor - very gently 3,5 wet - - -

218 73,5998 117,2295 10. 08Log floor - very gently 3,5 wet - - -

219 73,6104 117,1347 11. 08Tidal flat lower plain - flat 1,5 wet surface water 5 -

220 73,6085 117,1544 11. 08Tidal flat lower plain - flat 1,5 wet surface water 5 -

221 73,6083 117,1561 11. 08Tidal flat lower plain - flat 1,5 wet surface water 5 -

224 73,6104 117,1346 12. 08Log floor - flat 2 very moist - - -

243 73,6083 117,1540 12. 08Log floor - flat 2 very moist - - -

262 73,6069 117,1821 12. 08Log lower slope - very gently 4 moist - - -

266 73,6073 117,1879 12. 08Ovrag medium slope mud flows steep 50 very moist - - -

Mak-1 73,6074 117,1892 12. 08Cliff lower slope mud flows very steep 80 wet - - yes

Mak-2 73,6075 117,1825 14. 08Cliff lower slope mud flows very steep 70 wet - - yes

Mak-3 73,6075 117,1819 14. 08Cliff lower slope mud flows very steep 75 wet - - yes

275 73,6043 117,1334 15. 08Log floor - very gently 3 wet surface water 5 -

276 73,6058 117,1355 15. 08Log medium slope thermokarst hills gently 12 moist - - yes

277 73,6059 117,1501 15. 08Log medium slope - low 25 moist - - yes

278 73,6055 117,1493 15. 08Log medium slope - low 25 moist - - yes

279 73,6057 117,1601 15. 08Edoma upper slope thermokarst hills very gently 7,5 moderate moist - - yes 280 73,6058 117,1653 15. 08Edoma elevated plain polygonal structures flat 1 very moist

large irregular

polygonal pond 22 yes

281 73,6059 117,1713 15. 08Edoma elevated plain - flat 1 moist small ponds <40 yes

282 73,6035 117,1746 15. 08Edoma upper slope - gently 14 very moist - - yes

283 73,6023 117,1799 15. 08Edoma upper slope thermokarst hills moderate 18 moist - - yes

155

The Expedition Lena-Anabar 20034. Periglacial studies around Cape “Mamontov Klyk”

Appendix 4-1. Continuation

284 73,6015 117,1810 15. 08Log floor - flat 1 wet surface water 10 yes

285 73,6004 117,1808 15. 08Log floor - flat 1 wet large pond >50 yes

286 73,5990 117,1826 15. 08Edoma elevated plain polygonal structures flat 2 moist small ponds 12 yes 287 73,5983 117,1849 15. 08Edoma elevated plain polygonal structures flat 2 moist small ponds 12 yes

288 73,5967 117,1842 15. 08Log floor - flat 1 wet large pond 30 yes

289 73,5969 117,1829 15. 08Edoma medium slope thermokarst hills low 16 less moist - - -

290 73,5974 117,1749 15. 08Edoma upper slope - gently 7,5 moist - - -

291 73,5977 117,1697 15. 08Edoma medium slope - gently 13 less moist - - yes

292 73,5980 117,1619 15. 08Edoma elevated plain polygonal structures flat 1 moist

small polygonal

ponds n.a. yes 293 73,5983 117,1576 15. 08Edoma elevated plain polygonal structures flat 1 very moist large pond 20 yes 294 73,5988 117,1571 15. 08Edoma elevated plain polygonal structures flat 1 very moist

large irregular

polygonal pond n.a. yes

295 73,6096 117,1202 18. 08River valley terrace sand bank flat 1 moist - - yes

296 73,6104 117,1200 18. 08River valley terrace sand bank flat 1 moist - - yes

297 73,6118 117,1200 18. 08River valley terrace sand bank flat 2 moist - - yes

298 73,6077 117,1259 18. 08Edoma medium slope thermokarst hills low 25 less moist - - -

299 73,6075 117,1193 19. 08River valley terrace sand bank gently 4 very moist - - yes

300 73,6077 117,1151 19. 08River valley terrace sand bank flat 1 moist surface water 5 yes 301 73,6066 117,1072 19. 08Edoma medium slope thermokarst hills gently 12,5 less moist - - yes

300 73,6077 117,1151 19. 08River valley terrace sand bank flat 1 moist surface water 5 yes 301 73,6066 117,1072 19. 08Edoma medium slope thermokarst hills gently 12,5 less moist - - yes

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